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Stable Isotope-Based Reconstruction of Oligo-Miocene Paleoenvironment and Paleohydrology of Central Anatolian Lake Basins (Turkey)

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Stable Isotope-Based Reconstruction of Oligo-Miocene Paleoenvironment and Paleohydrology of Central Anatolian Lake Basins (Turkey) Turkish Journal of Earth Sciences Turkish J Earth Sci (2013) 22: 793-819 http://journals.tubitak.gov.tr/earth/ © TÜBİTAK Research Article doi:10.3906/yer-1207-11 Stable isotope-based reconstruction of Oligo-Miocene paleoenvironment and paleohydrology of Central Anatolian lake basins (Turkey) 1,2, 2,6 3 4 1,2,5 Tina LÜDECKE *, Tamás MIKES , F. Bora ROJAY , Michael A. COSCA , Andreas MULCH 1 Biodiversity and Climate Research Centre, Frankfurt, Germany 2 Institute of Geosciences, Goethe University Frankfurt, Frankfurt, Germany 3 Department of Geological Engineering, Faculty of Engineering, Middle East Technical University, Ankara, Turkey 4 US Geological Survey, Denver Federal Center, Denver, Colorado, USA 5 Senckenberg Research Institute and Natural History Museum, Frankfurt, Germany 6 Eriksfiord AS, Stavanger, Norway Received: 27.07.2012 Accepted: 28.01.2013 Published Online: 26.08.2013 Printed: 26.09.2013 Abstract: Isotope geochemistry of lacustrine carbonate represents a powerful tool to reconstruct paleoclimatic and paleoenvironmental conditions. Here, we present a comprehensive set of long-term oxygen (δ18O) and carbon (δ13C) stable isotope records from 5 Chattian to Burdigalian lacustrine sequences distributed over the Central Anatolian Plateau. Field relationships combined with stable isotope geochemistry indicate a relatively humid subtropic Late Oligocene climate with an environment characterized by large, temporally open freshwater lakes. Approximately during the middle Aquitanian, a 4‰–5‰ increase in lake δ18O values indicates changes in regional climate including more arid conditions and an increasing dominance of closed saline lake conditions in the central plateau region. This time period was also characterized by frequent climatic fluctuations such as short-lived humid periods, possibly recording the influence of seasonality, topography, and the waxing and waning of aridity. In general, relatively high Oligo-Miocene δ18O lake water values within the modern plateau interior, even for the least evaporative sequences, suggest the absence of significant orographic barriers at both the northern and southern plateau margins prior to 20–16 Ma. Key words: Cenozoic, lacustrine carbonates, stable isotopes, 40Ar/39Ar geochronology, Central Anatolian Plateau, Turkey 1. Introduction paleoenvironments in the Eastern Mediterranean to The Oligocene/Miocene represents a critical interval with better understand the vegetation and climate history of respect to the tectonic, geologic, and climatic history of the region. However, most of these studies are based on the Central Anatolian Plateau (CAP) prior to and during micro- and macrofloral records, either addressing spatially the uplift of the plateau margins. Fission-track evidence extensive coverage (e.g., Ivanov et al. 2002; Kovar-Eder et points to an initial phase of Late Oligocene to Middle al. 2006; Akgün et al. 2007; Bruch et al. 2007; Fauquette et Miocene uplift of the Western Pontides in the northwest al. 2007; Ivanov et al. 2007a, 2007b; Strömberg et al. 2007; of the plateau (Zattin et al. 2005; Okay et al. 2008; Cavazza Ivanov et al. 2008; Yavuz-Işık & Toprak 2010; Bruch et al. et al. 2012), whereas the still ongoing differential surface 2011; Ivanov et al. 2011; Utescher et al. 2011) or focusing uplift of the Central Pontides, which is mainly driven on more local records (e.g., Akgün 1993; Whateley & by the North Anatolian Fault Zone, started in the Late Tuncali 1995; Akgün & Sözbilir 1999; Karayiğit et al. 1999; Miocene to Early Pliocene (Yildirim et al. 2011). Equally Akgün et al. 2002; Akkiraz & Akgün 2005; Kayseri et al. important is the multiphased surface uplift history of the 2006). Other approaches use mammal fossils as climatic Central Taurides that border the CAP from the south, for proxies (e.g., Böhme 2003; Fortelius et al. 2006; Eronen et which Mediterranean slab dynamics appear to have played al. 2009) or are based on sedimentologic analysis, such as a fundamental driving role in triggering a rapid phase of tracing the presence of lignite as an indicator of a warm surface uplift post-8 Ma (Cosentino et al. 2012; Schildgen and wet climate (e.g., Yağmurlu et al. 1988; İnci 1990). et al. 2012a, 2012b). This work presents the first comprehensive long-term Oligo-Miocene continental basins cover a remarkably oxygen (δ18O) and carbon (δ13C) stable isotope analysis large area of the CAP (Figure 1). Numerous studies carried out on Middle Cenozoic continental successions were carried out to reconstruct Middle Cenozoic on the CAP. Lacustrine and pedogenic continental * Correspondence: [email protected] 793 LÜDECKE et al. / Turkish J Earth Sci Kızılcahamam Figure 1. Digital elevation map of Turkey with relevant geological and tectonic features and location of the studied sedimentary sequences. ECE: Ecemiş Corridor, MUT: Mut Basin, ILG: Ilgın Basin, GÖK: Gökler locality (Ankara region), KAS: Kasımlar locality (Ankara region). For geographic coordinates of the sampled sections, see Table 1; for field photographs, see Figures 2, 3, and 4. carbonate deposits are ubiquitous on the modern plateau such as water residence time, water balance, origin and and represent a premier framework for reconstructing composition of meteoric waters, sediment input, and Late Oligocene and Early Miocene paleoenvironments of climate changes such as fluctuations in precipitation the region. One of the main obstacles in reconstructing (e.g., Tucker & Wright 1990; Leng & Marshall 2004; past environmental conditions on the CAP, however, is the Gierlowski-Kordesch 2010). Provided that adequate scarcity of high-precision chronological constraints. Ages of age control is available, lacustrine carbonate deposited the sequences documented here are therefore based in part in such environments is capable of tracking some on published biostratigraphic and magnetostratigraphic of this information and hence represents a valuable data as well as new 40Ar/39Ar geochronology of intercalated paleoenvironmental record. ash layers. Lake waters are part of the meteoric water cycle. The 18 18 13 δ O and δ C data from Chattian to Burdigalian oxygen isotopic composition of meteoric waters (δ Omw) paleolakes of the CAP indicate a long-term overall increase is affected by many factors, with the most important in lacustrine oxygen and carbon isotopic ratios over fractionation mechanisms for water being evaporation and time, with younger successions displaying an increased condensation at the hydrosphere–atmosphere interface positive covariance between δ13C and δ18O. Together with (Horita & Wesolowski 1994). The δ18O of lake water (δ18O ) is influenced by the field indicators of aridity (e.g., desiccation cracks) such a lw oxygen isotopic composition of meteoric waters supplied δ18O – δ13C covariance suggests a shift towards more arid to the lake, such as precipitation, surface runoff, and conditions during the Early Miocene. This trend may be groundwater inflow. Evaporation, itself governed by episodically interrupted by phases of increased humidity, temperature and relative humidity, strongly controls the especially during the Aquitanian when frequent climatic depletion in the light oxygen isotope 16O in the water (rainfall) fluctuations seem to have been common. phase. Changes in temperature, rainfall sources, riverine influx, and groundwater input are retained in the oxygen 2. Isotopic compositions of lake sediments 18 isotope ratios of carbonates (δ Ocarb) which precipitate 2.1. Stable oxygen isotope geochemistry from lake water (e.g., Turner et al. 1983; Talbot 1990; In contrast to marine environments, which are buffered Teranes et al. 1999; Lamb et al. 2000; Schwalb & Dean 2002; physically and chemically against minor environmental Leng & Marshall 2004; Yansa et al. 2007; Davis et al. 2009; changes, lakes represent highly sensitive and dynamic Deocampo 2010; Kent-Corson et al. 2010). Stratigraphic 18 systems, with the potential to record changes in hydrology changes in δ Ocarb values of lacustrine sections can 794 LÜDECKE et al. / Turkish J Earth Sci therefore be attributed to changes in temperature or a Thermo Delta V mass spectrometer at the Institute of 18 δ Olw (Leng & Marshall 2004). Lacustrine carbonate Geology, University of Hannover, as well as a Thermo MAT oxygen isotope records have been also used in isotope- 253 mass spectrometer at the Institute of Geosciences, based paleoelevation models exploiting the systematic University of Frankfurt. Both instruments were interfaced relationship between oxygen isotopes in precipitation and to a Thermo GasBench II. Analytical procedures followed surface elevation (e.g., Currie et al. 2005; Garzione et al. those of Spötl and Vennemann (2003). Raw isotopic ratios 2008; Mix et al. 2011; Campani et al. 2012). were calibrated against a Carrara marble in-house standard A common obstacle in assessing all such 18 as well as against NBS18 and NBS19 carbonate reference paleoenvironmental conditions is that δ Olw does not 18 materials. Final isotopic ratios are reported against necessarily reflect the primary composition of δ Omw; 18 13 it is therefore important to account for evaporation, the V-SMOW (δ O) and V-PDB (δ C). Overall analytical residence time of the lake water, and biogeochemical uncertainties on the isotopic ratios are better than 0.07‰ 18 13 18 absolute (δ O) and 0.04‰ absolute (δ C). Carbonate processes in the lake that potentially affect δ Olw (and δ13C) (Fronval et al. 1995; Cyr et al. 2005). Likewise, size contents were derived from standard-sample
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